Mount St. Helens

Mount St. Helens is 55 km west of Mount Adams, in the western part of the Cascade Range. Considered “brother and sister” mountains, the two volcanoes are approximately 80 km from Mount Rainier, the highest of the Cascade volcanoes. Mount Hood, the nearest major volcanic peak in Oregon, is 100 km southeast of Mount St. Helens.

Mount St. Helens is geologically young compared with the other major Cascade volcanoes. It formed only within the past 40,000 years, and the summit cone present before its 1980 eruption began rising about 2,200 years ago. The volcano is considered the most active in the Cascades within the Holocene epoch, which encompasses roughly the last 10,000 years.

Prior to the 1980 eruption, Mount St. Helens was the fifth-highest peak in Washington. It stood out prominently from surrounding hills because of the symmetry and extensive snow and ice cover of the pre-1980 summit cone, earning it the nickname, by some, “Fuji-san of America”.

The peak rose more than 1,500 m above its base, where the lower flanks merged with adjacent ridges. The mountain is 9.7 km across at its base, which is at an elevation of 1,300 m on the northeastern side and 1,200 m elsewhere. At the pre-eruption tree line, the width of the cone was 6.4 km.

Streams that originate on the volcano enter three main river systems: The Toutle River on the north and northwest, the Kalama River on the west, and the Lewis River on the south and east. The streams are fed by abundant rain and snow.

The average annual rainfall is 360 cm, and the snowpack on the mountain’s upper slopes can reach 4.9 m. The Lewis River is impounded by three dams for hydroelectric power generation. The southern and eastern sides of the volcano drain into an upstream impoundment, the Swift Reservoir, which is directly south of the volcano’s peak.

Although Mount St. Helens is in Skamania County, Washington, access routes to the mountain run through Cowlitz County to the west, and Lewis County to the north. State Route 504, locally known as the Spirit Lake Memorial Highway, connects with Interstate 5 at Exit 55 km to the west of the mountain.

That north-south highway skirts the low-lying cities of Castle Rock, Longview, and Kelso along the Cowlitz River, and passes through the Vancouver, Washington–Portland, Oregon metropolitan area less than 80 km to the southwest. The community nearest the volcano is Cougar, Washington, in the Lewis River valley 18 km south-southwest of the peak. Gifford Pinchot National Forest surrounds Mount St. Helens.

During the winter of 1980–1981, a new glacier appeared. Now officially named Crater Glacier, it was formerly known as the Tulutson Glacier. Shadowed by the crater walls and fed by heavy snowfall and repeated snow avalanches, it grew rapidly (4.3 m) per year in thickness).

By 2004, it covered about 0.93 km2 and was divided by the dome into a western and eastern lobe. Typically, by late summer, the glacier looks dark from rockfall from the crater walls and ash from eruptions.

As of 2006, the ice had an average thickness of 100 m and a maximum of 200 m, nearly as deep as the much older and larger Carbon Glacier of Mount Rainier.

The ice is all post-1980, making the glacier very young geologically. However, the volume of the new glacier is about the same as all the pre-1980 glaciers combined.

With the recent volcanic activity starting in 2004, the glacier lobes were pushed aside and upward by the growth of new volcanic domes. The surface of the glacier, once mostly without crevasses, turned into a chaotic jumble of icefalls heavily crisscrossed with crevasses and seracs caused by the movement of the crater floor.

The new domes have almost separated the Crater Glacier into an eastern and western lobe. Despite the volcanic activity, the termini of the glacier have still advanced, with a slight advance on the western lobe and a more considerable advance on the more shaded eastern lobe. Due to the advance, two lobes of the glacier joined in late May 2008 and thus the glacier completely surrounds the lava domes.

In addition, since 2004, new glaciers have formed on the crater wall above Crater Glacier feeding rock and ice onto its surface below; there are two rock glaciers to the north of the eastern lobe of Crater Glacier.

Mount St. Helens is part of the Cascades Volcanic Province, an arc-shaped band extending from southwestern British Columbia to Northern California, roughly parallel to the Pacific coastline. Beneath the Cascade Volcanic Province, a dense oceanic plate sinks beneath the North American Plate; a process known as subduction (geology).

As the oceanic slab sinks deep into the Earth’s interior beneath the continental plate, high temperatures and pressures allow water molecules locked in the minerals of solid rock to escape. The water vapor rises into the pliable mantle above the subducting plate, causing some of the mantle to melt.

This newly formed magma ascends upward through the crust along a path of least resistance, both by way of fractures and faults as well as by melting wall rocks. The addition of melted crust changes the geochemical composition. Some of the melt rises toward the Earth’s surface to erupt, forming the Cascade Volcanic Arc above the subduction zone.

The magma from the mantle has accumulated in two chambers below the volcano: one approximately 5–12 kilometers below the surface, the other about 12–40 kilometers. The lower chamber may be shared with Mount Adams and the Indian Heaven volcanic field.

Ancestral stages of eruptive activity

The early eruptive stages of Mount St. Helens are known as the “Ape Canyon Stage” (around 40,000–35,000 years ago), the “Cougar Stage” (ca. 20,000–18,000 years ago), and the “Swift Creek Stage” (roughly 13,000–8,000 years ago). The modern period, since about 2500 BCE, is called the “Spirit Lake Stage”.

Collectively, the pre–Spirit Lake stages are known as the “ancestral stages”. The ancestral and modern stages differ primarily in the composition of the erupted lavas; ancestral lavas consist of a characteristic mixture of dacite and andesite, while modern lava is very diverse (ranging from olivine basalt to andesite and dacite).

St. Helens started its growth in the Pleistocene 37,600 years ago, during the Ape Canyon stage, with dacite and andesite eruptions of hot pumice and ash. Thirty-six thousand years ago a large mud flow cascaded down the volcano;  mudflows were significant forces in all of St. Helens’ eruptive cycles.

The Ape Canyon eruptive period ended around 35,000 years ago and was followed by 17,000 years of relative quiet. Parts of this ancestral cone were fragmented and transported by glaciers 14,000–18,000 years ago during the last glacial period of the current ice age.

The second eruptive period, the Cougar Stage, started 20,000 years ago and lasted for 2,000 years.  Pyroclastic flows of hot pumice and ash along with dome growth occurred during this period.

Another 5,000 years of dormancy followed, only to be upset by the beginning of the Swift Creek eruptive period, typified by pyroclastic flows, dome growth, and blanketing of the countryside with tephra. Swift Creek ended 8,000 years ago.

Smith Creek and Pine Creek eruptive periods

A dormancy of about 4,000 years was broken around 2500 BCE with the start of the Smith Creek eruptive period when eruptions of large amounts of ash and yellowish-brown pumice covered thousands of square miles.

An eruption in 1900 BCE was the largest known eruption from St. Helens during the Holocene epoch, depositing the Yn tephra. This eruptive period lasted until about 1600 BCE and left 46 cm deep deposits of material 80 km distant in what is now Mount Rainier National Park.

Trace deposits have been found as far northeast as Banff National Park in Alberta, and as far southeast as eastern Oregon. All told there may have been up to 10 km3 of material ejected in this cycle.  Some 400 years of dormancy followed.

St. Helens came alive again around 1200 BCE — the Pine Creek eruptive period.  This lasted until about 800 BCE and was characterized by smaller-volume eruptions. Numerous dense, nearly red hot pyroclastic flows sped down St. Helens’ flanks and came to rest in nearby valleys. A large mudflow partly filled 64 km of the Lewis River valley sometime between 1000 BCE and 500 BCE.

Castle Creek and Sugar Bowl eruptive periods

The next eruptive period, the Castle Creek period, began about 400 BCE and is characterized by a change in the composition of St. Helens’ lava, with the addition of olivine and basalt.

The pre-1980 summit cone started to form during the Castle Creek period. Significant lava flows in addition to the previously much more common fragmented and pulverized lavas and rocks (tephra) distinguished this period. Large lava flows of andesite and basalt covered parts of the mountain, including one around the year 100 BCE that traveled all the way into the Lewis and Kalama river valleys.

Others, such as Cave Basalt (known for its system of lava tubes), flowed up to 14 km from their vents.  During the first century, mudflows moved 50 km down the Toutle and Kalama river valleys and may have reached the Columbia River. Another 400 years of dormancy ensued.

The Sugar Bowl eruptive period was short and markedly different from other periods in Mount St. Helens history. It produced the only unequivocal laterally directed blast known from Mount St. Helens before the 1980 eruptions.

During Sugar Bowl time, the volcano first erupted quietly to produce a dome, then erupted violently at least twice producing a small volume of tephra, directed-blast deposits, pyroclastic flows, and lahars.

Kalama and Goat Rocks eruptive periods

Roughly 700 years of dormancy were broken in about 1480, when large amounts of pale gray dacite pumice and ash started to erupt, beginning the Kalama period. The eruption in 1480 was several times larger than the May 18, 1980 eruption. In 1482, another large eruption rivaling the 1980 eruption in volume is known to have occurred.

Ash and pumice piled 9.7 km northeast of the volcano to a thickness of 0.9 m; 80 km away, the ash was 5 cm deep. Large pyroclastic flows and mudflows subsequently rushed down St. Helens’ west flanks and into the Kalama River drainage system.

This 150-year period next saw the eruption of less silica-rich lava in the form of andesitic ash that formed at least eight alternating light- and dark-colored layers.  Blocky andesite lava then flowed from St. Helens’ summit crater down the volcano’s southeast flank.

Later, pyroclastic flows raced down over the andesite lava and into the Kalama River valley. It ended with the emplacement of a dacite dome ~200 m high at the volcano’s summit, which filled and overtopped an explosion crater already at the summit.

Large parts of the dome’s sides broke away and mantled parts of the volcano’s cone with talus. Lateral explosions excavated a notch in the southeast crater wall. St. Helens reached its greatest height and achieved its highly symmetrical form by the time the Kalama eruptive cycle ended, in about 1647.  The volcano remained quiet for the next 150 years.

The 57-year eruptive period that started in 1800 was named after the Goat Rocks dome and is the first time that both oral and written records exist.  Like the Kalama period, the Goat Rocks period started with an explosion of dacite tephra, followed by an andesite lava flow, and culminated with the emplacement of a dacite dome.

The 1800 eruption probably rivaled the 1980 eruption in size, although it did not result in massive destruction of the cone. The ash drifted northeast over central and eastern Washington, northern Idaho, and western Montana. There were at least a dozen reported small eruptions of ash from 1831 to 1857, including a fairly large one in 1842.

The vent was apparently at or near Goat Rocks on the northeast flank.  Goat Rocks dome was the site of the bulge in the 1980 eruption, and it was obliterated in the major eruption event on May 18, 1980, that destroyed the entire north face and top 400 m of the mountain.

1980 to 2001 activity

On March 20, 1980, Mount St. Helens experienced a magnitude 4.2 earthquake; and, on March 27, steam venting started. By the end of April, the north side of the mountain had started to bulge. On May 18, a second earthquake, of magnitude 5.1, triggered a massive collapse of the north face of the mountain. It was the largest known debris avalanche in recorded history.

The magma in St. Helens burst forth into a large-scale pyroclastic flow that flattened vegetation and buildings over 600 km2. More than 1.5 million metric tons of sulfur dioxide were released into the atmosphere. On the Volcanic Explosivity Index scale, the eruption was rated a 5, and categorized as a Plinian eruption.

The collapse of the northern flank of St. Helens mixed with ice, snow, and water to create lahars (volcanic mudflows). The lahars flowed many miles down the Toutle and Cowlitz Rivers, destroying bridges and lumber camps. A total of 3,000,000 m3 of material was transported 27 km south into the Columbia River by the mudflows.

For more than nine hours, a vigorous plume of ash erupted, eventually reaching 20 to 27 km above sea level. The plume moved eastward at an average speed of 100 km/h with ash reaching Idaho by noon. Ashes from the eruption were found collecting on top of cars and roofs the next morning as far as the city of Edmonton in Alberta, Canada.

By about 5:30 p.m. on May 18, the vertical ash column declined in stature, and less severe outbursts continued through the night and for the next several days. The St. Helens May 18 eruption released 24 megatons of thermal energy; it ejected more than 2.79 km3 of material.

The removal of the north side of the mountain reduced St. Helens’ height by about 400 m and left a crater 1.6 km to 3.2 km wide and 600 m deep, with its north end open in a huge breach. The eruption killed 57 people, nearly 7,000 big game animals (deer, elk, and bear), and an estimated 12 million fish from a hatchery. It destroyed or extensively damaged over 200 homes, 298 km of the highway, and 24 km of railways.

Between 1980 and 1986, activity continued at Mount St. Helens, with a new lava dome forming in the crater. Numerous small explosions and dome-building eruptions occurred. From December 7, 1989, to January 6, 1990, and from November 5, 1990, to February 14, 1991, the mountain erupted with sometimes huge clouds of ash.

2004 to 2008 activity

Magma reached the surface of the volcano about October 11, 2004, resulting in the building of a new lava dome on the existing dome’s south side. This new dome continued to grow throughout 2005 and into 2006.

Several transient features were observed, such as a lava spine nicknamed the “whaleback”, which comprised long shafts of solidified magma being extruded by the pressure of magma beneath.

These features were fragile and broke down soon after they were formed. On July 2, 2005, the tip of the whaleback broke off, causing a rockfall that sent ash and dust several hundred meters into the air.

Mount St. Helens showed significant activity on March 8, 2005, when a 36,000-foot (11,000 m) plume of steam and ash emerged — visible from Seattle.[38] This relatively minor eruption was a release of pressure consistent with ongoing dome building. The release was accompanied by a magnitude 2.5 earthquake.

Another feature to emerge from the dome was called the “fin” or “slab”. Approximately half the size of a football field, the large, cooled volcanic rock was being forced upward as quickly as 2 m per day.

In mid-June 2006, the slab was crumbling in frequent rockfalls, although it was still being extruded. The height of the dome was 2,300 m, still below the height reached in July 2005 when the whaleback collapsed.

On October 22, 2006, at 3:13 PM PST, a magnitude 3.5 earthquake broke loose Spine 7. The collapse and avalanche of the lava dome sent an ash plume 600 m over the western rim of the crater; the ash plume then rapidly dissipated.

On December 19, 2006, a large white plume of condensing steam was observed, leading some media people to assume there had been a small eruption. However, the Cascades Volcano Observatory of the USGS did not mention any significant ash plume. The volcano was in a continuous eruption from October 2004, but this eruption consisted in large part of a gradual extrusion of lava forming a dome in the crater.

On January 16, 2008, steam began seeping from a fracture on top of the lava dome. Associated seismic activity was the most noteworthy since 2004. Scientists suspended activities in the crater and the mountain flanks, but the risk of a major eruption was deemed low.

By the end of January, the eruption paused; no more lava was being extruded from the lava dome. On July 10, 2008, it was determined that the eruption had ended, after more than six months of no volcanic activity.

Future hazards

Future eruptions of Mount St. Helens will likely be even larger than the 1980 eruption.  The current configuration of lava domes in the crater means that much more pressure will be required for the next eruption, and hence the level of destruction will be higher.

Significant ashfalls may spread over 100,000 km2, disrupting transportation.  A large lahar flow is likely on branches of the Toutle River, possibly causing destruction in inhabited areas along the I-5 corridor.

In its undisturbed state, the slopes of Mount St. Helens lie in the Western Cascades Montane Highlands ecoregion. This ecoregion has abundant precipitation: an average of 2,373 mm of precipitation falls each year at Spirit Lake. This precipitation supported dense forest up to 1,600 m, with western hemlock, Douglas-fir, and western redcedar. Above this, this forest was dominated by Pacific silver fir up to 1,300 m.

Finally, below the treeline, the forest consisted of mountain hemlock, Pacific silver fir, and Alaska yellow cedar. Large mammals included Roosevelt elk, black-tailed deer, American black bear, and mountain lion.

Treeline at Mount St Helens was unusually low, at about 1,340 m. This was due to prior volcanic disturbance of the forest: the treeline was thought to be moving up the slopes before the eruption.[46] Alpine meadows were uncommon at Mount St Helens. Mountain goats inhabited higher elevations of the peak, although they were wiped out in the 1980 eruption.

The ecological disturbance caused by the eruption

The Mount St. Helens eruption has the most ecological study of an eruption, because research into disturbance commenced immediately after the eruption, and because the eruption did not sterilize the immediate area. More than half of the papers on ecological response to volcanic eruption came from studies at Mount St. Helens.

The most important ecological concept that came from the study at Mount St. Helens is biological legacy. Biological legacies are the survivors of catastrophic disturbance: they can either be alive (e.g., plants that survive ashfall or pyroclastic flow), organic debris, or biotic patterns left over from before the disturbance. These biological legacies highly influence the re-establishment of the post-disturbance ecology.

Importance to indigenous tribes

Native American lore contains numerous stories to explain the eruptions of Mount St. Helens and other Cascade volcanoes. The most famous of these is the Bridge of the Gods story told by the Klickitat people.

In the story, the chief of all the gods and his two sons, Pahto (also called Klickitat) and Wy’east, traveled down the Columbia River from the Far North in search of a suitable area to settle.

They came upon an area that is now called The Dalles and thought they had never seen a land so beautiful. The sons quarreled over the land, so to solve the dispute their father shot two arrows from his mighty bow – one to the north and the other to the south.

Pahto followed the arrow to the north and settled there while Wy’east did the same for the arrow to the south. The chief of the gods then built the Bridge of the Gods, so his family could meet periodically.

When the two sons of the chief of the gods fell in love with a beautiful maiden named Loowit, she could not choose between them. The two young chiefs fought over her, burying villages and forests in the process. The area was devastated and the earth shook so violently that the huge bridge fell into the river, creating the cascades of the Columbia River Gorge.

For punishment, the chief of the gods struck down each of the lovers and transformed them into great mountains where they fell. Wy’east, with his head lifted in pride, became the volcano known today as Mount Hood. Pahto, with his head bent toward his fallen love, was turned into Mount Adams. The beautiful Loowit became Mount St. Helens, known to the Klickitats as Louwala-Clough, which means “smoking or fire mountain” in their language (the Sahaptin call the mountain Loowit).

The mountain is also of sacred importance to the Cowlitz and Yakama tribes that also live in the area. They find the area above its tree line to be of exceptional spiritual significance, and the mountain (which they call “Lawetlat’la”, roughly translated as “the smoker”) features prominently in their creation story, and in some of their songs and rituals.

In recognition of its cultural significance, over 4,900 ha of the mountain (roughly bounded by the Loowit Trail) have been listed on the National Register of Historic Places.

Other area tribal names for the mountain include “nšh´ák´” (“water coming out”) from the Upper Chehalis, and “aka akn” (“snow mountain”), a Kiksht term.

Exploration by Europeans

Royal Navy Commander George Vancouver and the officers of HMS Discovery made the Europeans’ first recorded sighting of Mount St. Helens on 19 May 1792, while surveying the northern Pacific Ocean coast. Vancouver named the mountain for British diplomat Alleyne Fitzherbert, 1st Baron St Helens on 20 October 1792, as it came into view when the Discovery passed into the mouth of the Columbia River.

Years later, explorers, traders, and missionaries heard reports of an erupting volcano in the area. Geologists and historians determined much later that the eruption took place in 1800, marking the beginning of the 57 year-long Goat Rocks Eruptive Period (see geology section).  Alarmed by the “dry snow,” the Nespelem tribe of northeastern Washington supposedly danced and prayed rather than collecting food and suffered during that winter from starvation.

In late 1805 and early 1806, members of the Lewis and Clark Expedition spotted Mount St. Helens from the Columbia River but did not report either an ongoing eruption or recent evidence of one.

They did however report the presence of quicksand and clogged channel conditions at the mouth of the Sandy River near Portland, suggesting an eruption by Mount Hood sometime in the previous decades.

In 1829 Hall J. Kelley led a campaign to rename the Cascade Range as the President’s Range and also to rename each major Cascade mountain after a former President of the United States. In his scheme, Mount St. Helens was to be renamed Mount Washington.

European colonization and use of the area

The first authenticated non-Indigenous eyewitness report of a volcanic eruption was made in March 1835 by Meredith Gairdner, while working for the Hudson’s Bay Company stationed at Fort Vancouver.

He sent an account to the Edinburgh New Philosophical Journal, which published his letter in January 1836. James Dwight Dana of Yale University, while sailing with the United States Exploring Expedition, saw the quiescent peak from off the mouth of the Columbia River in 1841. Another member of the expedition later described “cellular basaltic lavas” at the mountain’s base.

In the late fall or early winter of 1842, nearby European settlers and missionaries witnessed the so-called Great Eruption. This small-volume outburst created large ash clouds, and mild explosions followed for 15 years.

The eruptions of this period were likely phreatic (steam explosions). Josiah Parrish in Champoeg, Oregon witnessed Mount St. Helens in eruption on 22 November 1842. Ash from this eruption may have reached The Dalles, Oregon, 80 km southeast of the volcano.

In October 1843, future California governor Peter H. Burnett recounted a very likely apocryphal story of an Indigenous man who badly burned his foot and leg in lava or hot ash while hunting for deer. The story went that the injured man sought treatment at Fort Vancouver, but the contemporary fort commissary steward, Napoleon McGilvery, disclaimed knowledge of the incident.

British lieutenant Henry J. Warre sketched the eruption in 1845, and two years later Canadian painter Paul Kane created watercolors of the gently smoking mountain. Warre’s work showed erupting material from a vent about a third of the way down from the summit on the mountain’s west or northwest side (possibly at Goat Rocks), and one of Kane’s field sketches shows smoke emanating from about the same location.

On April 17, 1857, the Republican, a Steilacoom, Washington, newspaper, reported that “Mount St. Helens, or some other mount to the southward, is seen … to be in a state of eruption”.  The lack of a significant ash layer associated with this event indicates that it was a small eruption. This was the first reported volcanic activity since 1854.

Before the 1980 eruption, Spirit Lake offered year-round recreational activities. In the summer there was boating, swimming, and camping, while in the winter there was skiing.

The human impact from the 1980 eruption

Fifty-seven people were killed during the eruption. Had the eruption occurred one day later, when loggers would have been at work, rather than on a Sunday, the death toll could have been much higher.

Eighty-three-year-old Harry R. Truman, who had lived near the mountain for 54 years, became famous when he decided not to evacuate before the impending eruption, despite repeated pleas by local authorities. His body was never found after the eruption.

Another victim of the eruption was 30-year-old volcanologist David A. Johnston, who was stationed on the nearby Coldwater Ridge. Moments before his position was hit by the pyroclastic flow, Johnston radioed his famous last words: “Vancouver! Vancouver! This is it!” Johnston’s body was never found.

U.S. President Jimmy Carter surveyed the damage and said, “Someone said this area looked like a moonscape. But the moon looks more like a golf course compared to what’s up there.”

A film crew, led by Seattle filmmaker Otto Seiber, was dropped by helicopter on St. Helens on May 23 to document the destruction. Their compasses, however, spun in circles and they quickly became lost.

A second eruption occurred on May 25, but the crew survived and was rescued two days later by National Guard helicopter pilots. Their film, The Eruption of Mount St. Helens, later became a popular documentary.

The eruption had negative effects beyond the immediate area of the volcano. Ashfall caused approximately $100 million of damage to agriculture downwind in Eastern Washington.

The eruption also had positive impacts on society. Apple and wheat production were higher in the 1980 growing season, possibly due to ash helping to retain moisture in the soil. The ash was also a source of income: it was the raw material for the artificial gemstone helenite, or for ceramic glazes, or sold as a tourist curio.

In 1982, President Ronald Reagan and the U.S. Congress established the Mount St. Helens National Volcanic Monument, a 45,000 ha area around the mountain and within the Gifford Pinchot National Forest.

Following the 1980 eruption, the area was left to gradually return to its natural state. In 1987, the U.S. Forest Service reopened the mountain to climb. It remained open until 2004 when renewed activity caused the closure of the area around the mountain.

Most notable was the closure of the Monitor Ridge trail, which previously let up to 100 permitted hikers per day climb to the summit. On July 21, 2006, the mountain was again opened to climbers. In February 2010, a climber died after falling from the rim into the crater.

Mount St. Helens is a popular climbing destination for both beginning and experienced mountaineers. The peak is climbed year-round, although it is more often climbed from late spring through early fall.

All routes include sections of steep, rugged terrain. A permit system has been in place for climbers since 1987. A climbing permit is required year-round for anyone who will be above 1,500 m on the slopes of Mount St. Helens.

The standard hiking/mountaineering route in the warmer months is the Monitor Ridge Route, which starts at the Climbers Bivouac. This is the most popular and crowded route to the summit in the summer and gains about 1,400 m in approximately 8 km to reach the crater rim.

Although strenuous, it is considered a non-technical climb that involves some scrambling. Most climbers complete the round trip in 7 to 12 hours.

The Worm Flows Route is considered the standard winter route on Mount St. Helens, as it is the most direct route to the summit. The route gains about 1,700 m in elevation over about 10 km from trailhead to summit but does not demand the technical climbing that some other Cascade peaks like Mount Rainier do.

The route name refers to the rocky lava flows that surround the route. This route can be accessed via the Marble Mountain Sno-Park and the Swift Ski Trail.

The mountain is now circled by the Loowit Trail at elevations of 1,200–1,500 m. The northern segment of the trail from the South Fork Toutle River on the west to Windy Pass on the east is a restricted zone where camping, biking, pets, fires, and off-trail excursions are all prohibited.

On April 14, 2008, John Slemp, a snowmobiler from Damascus, Oregon, fell 457 meters into the crater after a snow cornice gave way beneath him on a trip to the volcano with his son. Despite his long fall, Slemp survived with minor injuries and was able to walk after coming to a stop at the foot of the crater wall, where he was rescued by a mountain rescue helicopter.

A visitor center run by the Washington State Parks is in Silver Lake, Washington, about 48 km west of Mount St. Helens. Exhibits include a large model of the volcano, a seismograph, a theater program, and an outdoor nature trail.